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Taberna Fm Tc LÉXICO ESTRATIGRÁFICO DE MÉXICO Taberna, formación…………………..………..Jurásico Medio (Bajociano temprano-tardío) Referencia(s): Erben, H.K., 1956a, El Jurásico Medio y el Caloviano de México, en XX Congreso Geológico Internacional, México, D.F., Monografía, 140 p. Historia nomenclatural de la unidad: Erben (1956a) propone de manera informal esta unidad y la incluye dentro del grupo Tecocoyunca (que contiene además a las unidades, Zorrillo, Simón, Otatera y Yucuñuti). Localidad tipo: Se ubica en la falda de la Loma de la Tierra Amarilla, en el lado sur del Arroyo de la Taberna al noreste de San Juan Diquiyú en la región de Tezoatlán, Oaxaca (Erben, 1956a), la sección tipo de acuerdo con Sandoval y Westermann (1986) se ubica en este sitio y mide 94 m. Descripción litológica: Erben (1956a, 1956b) describe esta unidad como lutita oscura con concreciones esferoidales de 1.5-5 cm de diámetro, lutita calcárea oscura con abundantes concreciones calcáreas esféricas de 5-25 cm de diámetro, bancos de caliza aislados con trigonias, intercalados con caliza oscura, depósitos margosos, limolita oscura con galerías de gusanos cuyo diámetro es menor a 1 mm y arenisca de grano fino con estratificación muy delgada. Lázaro-Larrabe y Cárdenas (1982) y Cárdenas- López (1983) señalan la presencia de mantos de carbón en la parte superior de esta unidad. Sandoval y Westermann (1986) mencionan que esta unidad en el centro oeste de Oaxaca está formada por lutita con intercalaciones de limolita y frecuentes concreciones ferruginosas con amonites. Espesores: Erben (1956a, 1956b) registra un espesor que varía entre 50-60 m, mientras que Sandoval y Westermann (1986) reportan que esta unidad varía de 50-100 m de espesor. Leyva-Rodríguez (1992) registra un espesor que varía de 30-50 m en las cercanías de San Juan Diquiyú. Distribución: Esta unidad aflora al noreste de Guerrero en la región de Cualac-Tecocoyunca donde es pobre en contenido fósil (Erben, 1956a; Westermann, 1981); localmente depósitos pertenecientes a esta unidad se encuentran en la barranca del arroyo Tecocoyunca en la falda occidental del cerro de Huamuxtitlán, en el valle del río Tlapaneco y sobre el río Tecoloyan en las cercanías de Totolapa (Lázaro-Larrabe y Cárdenas, 1982). Esta formación también se presenta al noroeste de Oaxaca en las regiones de Mixtepec, Tezoatlán-Diquiyú y de Diquiyú-Yutatio (Erben, 1956a; Ochoterena, 1963; Sandoval y Westermann, 1986). Relaciones estratigráficas: La formación Taberna sobreyace concordantemente a la formación Zorrillo y subyace de manera transicional y concordante a la formación Simón (Erben, 1956a; Carrasco-Ramírez, 1981; Westermann, 1981; Lázaro-Larrabe y Cárdenas, 1982; Cárdenas-López, 1983; Sandoval y Westermann, 1986; Leyva-Rodríguez, 1992). Erben (1956a) menciona que el contacto superior con la formación Simón, se encuentra caracterizado por la primera presencia de arenisca de grano grueso. Sandoval y Westermann (1986) mencionan que la formación Taberna gradúa a depósitos continentales o “semicontinentales” de las formaciones Simón y Otatera, mismas que de acuerdo con estos autores, con frecuencia no pueden ser diferenciadas (ver formaciones Simón y Otatera). Contenido paleontológico: Burckhardt (1927) estudió buena parte del material fósil (amonites) colectado en la región de Tezoatlán Oaxaca, aunque carece de información estratigráfica. (Erben, 1956a,b) menciona 1 LÉXICO ESTRATIGRÁFICO DE MÉXICO Se ha reportado para esta unidad la presencia de amonites pertenecientes a los géneros Stephanoceras, Oppelia (Erben, 1956a,b) y Dactylioceras (Erben, 1956b); así como, pelecípodos del género Trigonia (Erben, 1956a,b). Ochoterena (1963) propone al género Parastrenoceras en el cual incluye tres especies y dos subespecies (P. mixteca, P. mixteca mixteca, P. mixteca zapoteca, P. oaxacanum y P. tlaxiacense). Westermann (1981) reconoce la presencia de amonites pertenecientes a los géneros Leptosphinctes, Parastrenoceras y Oppelia. Lázaro-Larrabe y Cárdenas (1982) mencionan la abundancia de pelecípodos y fragmentos vegetales fósiles. Posteriormente, Sandoval y Westermann (1986) identifican además la presencia de los géneros Duashnoceras, Strigoceras, Stephanoceras, Phaulostephanus, Subcollina, Stephanosphinctes, así como las especies Subcollina lucretia, Stephanosphinctes buitroni y Phaulostephanus burckhardti de las cuales, estas dos últimas corresponden a nuevos taxa. Ambiente de depósito: Erben (1956a) infiere condiciones marinas durante el depósito de esta unidad. Carrasco-Ramírez (1981) interpreta que las condiciones de depósito que dieron origen a las formaciones Zorrillo y Taberna fueron de tipo costero y fluvial, los cuales pudieron formar parte de un complejo deltáico. Lázaro-Larrabe y Cárdenas (1982), Cárdenas-López (1983) propone que esta formación se depositó en una cuenca con circulación restringida, somera y condiciones reductoras variables mismas que pueden inferirse a partir de la presencia de pelitas rojizas y amarillentas; este autor añade que la cuenca se colmataba en ocasiones y ocurría la acumulación de depósitos continentales. Edad: Erben (1956a,b) con base en fauna de amonites, asignó a esta unidad una edad de Bajociano medio- tardío y Bajociano medio-Batoniano temprano respectivamente; sin embargo, el mismo autor reconoce controversias en la determinación taxonómica de los fósiles. Sandoval y Westermann (1986) reconocen la presencia de la Zona Duashnoceras floresi y de la Zona Parastrenoceras zapotecum, las cuales permiten a estos autores ubicar a esta unidad en un lapso que abarca de la parte alta del Bajociano temprano a la parte baja del Bajociano tardío. Dicha edad también es asignada por Jiménez-Rentería y Rueda-Gaxiola (2002) con base en su contenido fósil. Correlación: Carrasco-Ramírez (1981) infiere que esta unidad puede correlacionarse con las formaciones Etlaltongo y Yogaza de Oaxaca y con la formación Tecomazuchil de Puebla. Westermann (1981) propone la afinidad del conjunto de amonites identificado con la fauna del Tethys Occidental. Más adelante, Sandoval y Westermann (1986) basados en el conjunto de amonites estudiado, reconocen la afinidad biogeográfica con la provincia Mediterránea, así como con las provincias Andina y Cordillera del Norte, identificadas en el este del Pacífico; asimismo, reconocen dos biozonas para la parte centro oeste de Oaxaca y proponen su correlación con el esquema zonal europeo, así como con las biozonas reconocidas en Norte y Sudamérica. Importancia económica: Erben (1956a) reporta la presencia de un solo manto de carbón cerca de la mina Fundición del Sol de Mayo, en la región de Tlaxiaco, Oaxaca. Estudios posteriores enfocados a la identificación de yacimientos de carbón en la región comprendida entre el noreste de Guerrero y 2 LÉXICO ESTRATIGRÁFICO DE MÉXICO noroeste de Oaxaca fueron realizados por Díaz-Tapia et al. (1980), Díaz-Tapia y Hernández (1981), Lázaro-Larrabe y Cárdenas (1982) y Corona-Esquivel (1978). Estado nomenclatural: Esta unidad no cumple satisfactoriamente con todos los artículos para el establecimiento de unidades geológicas formales y publicaciones científicas adecuadas para tales fines (Artículos 3 y 4ab), por lo que constituye una unidad informal. Por tanto, se considera conveniente cumplir con los Procedimientos Generales para la Definición de Unidades Formales establecidos en el Código de Nomenclatura Estratigráfica (NASC, 2005; Artículos 3 a 16). Unidad analizada por: Juárez-Arriaga, E. Última actualización: Enero 2008. Citas bibliográficas: Burckhardt, C., 1927, Cefalópodos del Jurásico Medio de Oaxaca y Guerrero: Boletín del Instituto Geológico de México, (47), 108 p. Cárdenas-López, J.G., 1983, Prospección por carbón en la Cuenca Carbonífera de Cualac en el Estado de Guerrero: San Luís Potosí, S.L.P., México, Universidad Autónoma de San Luís Potosí, Escuela de Ingeniería, tesis profesional, 41 p. Carrasco-Ramírez, R.S., 1981, Geología Jurásica del área de Tlaxiaco, Mixteca Alta, Oaxaca: México, D.F., Universidad Nacional Autónoma de México, Faculta de Ciencias, tesis de maestría, 105 p. Corona-Esquivel, R., 1978, Estudio geológico de los depósitos carboníferos de la porción noreste del Estado de Guerrero: Chilpancingo, Gro., México, Consejo de Recursos Minerales, Archivo Técnico, 120221, 23 p. Díaz-Tapia, F.J., Flores-Aguillon, G., Velázquez-Sosa, E., Martínez-Amador, H., 1980: Informe geológico evaluativo de la Cuenca Carbonífera de Tlaxiaco, Oaxaca: Oaxaca, Oax., México, Consejo de Recursos Minerales, Archivo Técnico, 200131, 78 p. Díaz-Tapia F.J., Hernández, G.A., 1981, Estudio geológico de los depósitos carboníferos de la Cuenca de Cualac, en el Estado de Guerrero: Tlapa, Gro., México, Consejo de Recursos Minerales, Archivo Técnico, SIGMA-CRM TI 120131, 24 p. Erben, H.K., 1956a, El Jurásico Medio y el Caloviano de México, en XX Congreso Geológico Internacional, México, D.F., Monografía, 140 p. Erben, H.K., 1956b, Estratigrafía a lo largo de la carretera entre México, D.F. y Tlaxiaco, Oaxaca, con particular referencia a ciertas áreas de los estados de Puebla, Guerrero y Oaxaca en Maldonado-Koerdell (ed.), Estratigrafía y Paleontología del Mesozoico de la Cuenca Sedimentaria de Oaxaca y Guerrero, especialmente del Jurásico Inferior y Medio, XX Congreso Geológico Internacional, Excursión A-12, México, D.F., 11-36. Jiménez-Rentería, J., Rueda-Gaxiola, J., 2002, Reestructuración formal de los grupos Consuelo y Tecocoyunca (sensu Jorge Jiménez-Rentería), con base en el estudio palinoestratigráfico de las formaciones Conglomerado prieto y Conglomerado Cualac de la
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